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Stratigraphy of Lower Cambrian and Unconformable Lower Carboniferous Beds from the Valls Unit (Catalonian Coastal Ranges)

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Stratigraphy of Lower Cambrian and Unconformable Lower Carboniferous Beds from the Valls Unit (Catalonian Coastal Ranges) View metadata, citation and similar papers at core.ac.uk brought to you by CORE provided by Repositorio da Universidade da Coruña Pre-print from Comptes Rendus de l'Académie des Sciences, Paris, series IIA, Earth and Planetary Science, 330 (2000), 147-153. ISSN: 1251-329. http://www.sciencedirect.com/science/journal/12518050 Stratigraphie / Stratigraphy Stratigraphy of Lower Cambrian and unconformable lower Carboniferous beds from the Valls unit (Catalonian Coastal Ranges). Javier SANZ-LÓPEZ1, Joan-Carles MELGAREJO2, and Thomas Peter CRIMES3 ABSTRACT The Palaeozoic rocks outcropping around Valls are divided into two stratigraphic units. The boundary between both is an unconformity. The lower unit is composed by nearshore platform sediments and a Lower Cambrian age is indicated according to ichnotaxa content. The upper unit consists of pink nodular limestones and dark limestones, and it is followed by siliciclastic Culm Facies rocks. These limestones contain conodonts of the uppermost Tournaisian at its base (anchoralis-latus Zone) and lower Bashkirian (Namurian B) in the upper part. This condensed carbonate sequence was coeval with the thick siliciclastic Culm sedimentation in the surrounding areas. Keywords: Conodonts, Trace-fossils, Lower Cambrian, Carboniferous, Catalonian Coastal Ranges Stratigraphie des couches du Cambrien inférieur et des calcaires discordants du Carbonifère inférieur de l’unité de Valls (Chaînes Côtières Catalanes) RESUME Les roches paléozoïques qui affleurent près de Valls (Catalogne) sont divisées en deux unités stratigraphiques dont la limite est une discordance angulaire. L’unité inférieure est composée de sediments de plateforme côtière, d’âge Cambrien inférieur selon les ichnofossiles. L’unité supérieure, constituée de calcaires roses nodulaires et de calcaires foncés, est surmontée par des roches siliciclastiques de faciès Culm. La partie basale de ces calcaires contient des conodontes du Tournaisien supérieur (Zone à anchoralis-latus), alors que leur partie supérieure est du Bashkirien inférieur (Namurien B). Cette séquence carbonatée condensée est contemporaine d’une puissante sédimentation siliciclastique dans les zones périphériques. Mots-clés: Conodontes, Ichnofossiles, Cambrien inférieur, Carbonifère, Chaînes Catalanes Running title: Cambrian and Carboniferous from Valls, Catalonia VERSION ABREGEE Les roches qui forment l’unité de Valls (Melgarejo, 1992), ainsi que d’autres successions paléozoïques des Chaînes Côtières Catalanes, peuvent être divisées en une séquence pré-Carbonifère et une séquence Carbonifère, séparées par une discontinuité stratigraphique. Les affleurements de l’unité de Valls ont une extension réduite et discontinue au sud de la Serra de Miramar, secteur méridional des Chaînes Côtières Catalanes (figure 1). Cette unité est couverte par des roches post-hercyniennes au sud-ouest, tandis que ses autres limites correspondent à des failles. Ashauer et Teichmuller (1935) ont divisé la succession de l’unité de Valls en une partie inférieure constituée d’ardoises et de quartzites, et une partie supérieure formée de calcaires. Ces deux unités correspondent aux unités lithostratigraphiques de Picamoixons et Valls (figure 2) définies par Melgarejo (1992). Buchroithner (in Statteger, 1980) avait identifié quelques associations de conodontes dans les calcaires de l’unité de Valls (figure 3), correspondant à la limite Tournaisien/Viséen et au Viséen (Carbonifère inférieur). Une colonne synthétique (figure 2) a été réalisée à partir de différents affleurements de l’unité tectonique de Valls. L’unité inférieure de Picamoixons a une épaisseur d’environ 150 m, et est formée d’ardoises avec des intercalations de quartzites. Ces quartzites peuvent former des niveaux atteignant parfois 40 m d’épaisseur, tandis que la partie haute de l’unité est composée de couches centimétriques à métriques de grauwackes et quartzites, souvent bioturbées. Quelquefois on peut observer une stratification entrecroisée d’angle faible, des chenaux érosifs, des laminations horizontales, des granoclassements positifs, et plus rarement négatifes. La base de quelques couches peut présenter des grès de grain plus fin, des galets mous et des niveaux lenticulaires cimentés par des carbonates à coquilles de lingulides. Le sommet des couches peut avoir développé des rides d’oscillation et/ou des rides rectilignes. Les grès à grain fin et les siltites présentent une intense bioturbation, bien que les pistes récoltées soient pauvrement préservées. Parmi elles, on a déterminé Cruziana fasciculata, C. brannae et Rusophycus avalonensis, association qui indique un âge du Cambrien inférieur. Cruziana fasciculata et Rusophycus avalonensis ont été déterminés dans une formation d’âge probable correspondant au Tommotien supérieur-Atdabanien inférieur de Terre Neuve (Crimes et Anderson, 1985) et dans un horizon similaire des Grès de Herreria en la Zone Cantabrique (Crimes et al., 1977). L’unité stratigraphique de Valls se développe au-dessus d’une discordance angulaire dans le ravin oriental de Picamoixons, où les couches de quartzites de l’unité de Picamoixons sont inclinées de 15 degrés de plus (vers le nord- ouest) que les calcaires de la base de l’unité de Valls. La surface de contact est très irrégulière à l’échelle de l’affleurement, les sédiments calcaires emplissant les trous et fissures de l’alternance d’ardoises et de quartzites. Les premiers 15 centimètres de carbonates contiennent des clastes tabulaires de quartzites et des bioclastes enrobés par des enveloppes ferrugineuses. Les calcaires de Valls (environ 70 m) sont subdiviséés en deux sub-unités: A et B (figure 2). La partie inférieure de la sub-unité A est composée de calcaires mudstone pseudosparitiques nodulaires de couleur gris rosé, en couches décimétriques à métriques. Elles peuvent contenir des galets moux, des articles de tiges de crinoïdes et des restes de céphalopodes. La partie inférieure de l’ensemble est plus argileuse avec quelques niveaux de marne intercalés. La partie supérieur contient des calcaires gris-bleuté dont le dernier mètre est composé d’une alternance centimétrique de calcaires et marnes vertes. L’échantillon 1 (figures 2 et 3) récolté 15 cm au-dessus de la base de la sub-unité A, a donné des conodontes de la Zone à anchoralis- latus, Tournaisien supérieur/Viséen basal. L’échantillonage (2 et 3) nous a permis de mettre en évidence des associations appartenant à la Zone à texanus (Viséen inférieur) et à la Zone à L. nodosa, Viséen supérieur. La sous-unité B se caractérise par des calcaires mudstone gris massifs, en couches décimètriques; viennent ensuit des calcaires de couleur plus foncée. Ces calcaires foncés présentent des niveaux à nodules millimétriques silicifiés, et se trouvent au dessous de calcaires de couleur noire à lamination millimétrique, lesquels supportent des calcaires massifs. Les calcaires massifs présentent parfois des niveaux millimétriques à base irrégulière, érosive avec des accumulations de crinoïdes et d’autres bioclastes. Finalement, la série calcaire se termine par une alternance de 2 mètres d’épaisseur composée de calcaires mudstone nodulaires et de marnes, qui correspondent à la transition aux dépôts siliclastiques à Faciès Culm. L’échantillon 4 de l’ensemble B, contient les conodontes Idiognathoides macer, I. sulcatus et Paragnathodus glaber, alors que parmi les éléments de Idiognathoides de l’échantillon 5 on remarque I. attenuatus. Les deux associations peuvent être corrélées avec la Zone à I. sinuatus de Perret (1985, 1993) du Baskhirien inférieur des Pyrénées. L’échantillon 4 peut être assigné à l’étage Kinderscoutien ou Namurien B (R1), comme le révèle la présence de P. glaber, espèce citée dans des horizons du même âge dans les Montagnes Cantabriques (Méndez et Menéndez- Álvarez, 1985). La présence de I. attenuatus dans l’échantillon 5 signale un âge correspondant au moins au Marsdenien ou Namurien B (R2) trouvé en Angleterre (Higgins, 1975). Les caractères lithologiques et les ichnofaciès de l’unité de Picamoixons suggèrent un dépôt dans un environnement sublittoral avec développement de barres de sable. L’âge, selon les pistes identifiées, correspond au Cambrien inférieur. Des roches, avec des pistes attribuées au Cambrien des Chaînes Côtières Catalanes, ont seulement été mentionnées dans deux anciennes publications. Almera (1899) avait décrit des Bilobites (=Cruziana ?), trouvés dans des couches fines de quartzites et d’ardoises à Montcada (près de Barcelone). Dans le massif de Montseny (nord de Barcelone, figure 1B), des ardoises, des quartzites et des grauwackes (500 m) à Lingulella ferruginea ont été attribuées au Cambrien inférieur (Faura i Sans, 1913) et au Cambrien supérieur (Almera, 1913, in Ashauer & Teichmuller, 1935). Cet ensemble se trouve sur des marbres, lutites et cornubianites, et sous des ardoises grises bleutées (200 m). La position d’une unité d’ardoises et quartzites sur un intervalle d’ardoises avec des carbonates a été précédemment décrite par Melgarejo & Ayora (1990) dans l’anticlinal de Falset (Priorat, figure 1B). L’unité à quartzites correspondrait à l’unité de Picamoixons (Melgarejo, 1992) bien que, malheureusement, les pistes n’aient pas été rencontrées jusqu’à présent dans le secteur de Falset. Dans les Chaînes Côtières Catalanes, c’est uniquement dans le secteur de Valls qu’une discordance angulaire fossilisée par les calcaires du Tournaisien supérieur sur des roches cambriennes a été décrite. Dans le reste, des lydiennes et des ardoises du Tournaisien et localement du
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